Thesis; Thesis information not provided; 17 Jul 2003. / Published through the Information Bridge: DOE Scientific and Technical Information. "UCRL-LR-154423" Maxwell, R M; Tompson, A F B; Richardson, J H; El-Naser, H; Rihani, J. F F; Subah, A.; El Sha'r, W A; Al-Hadidi, Khair; Al-Awamleh, M; Al-Foqaha, M; Abu-Eid, O; Hayyaneh, R A. 07/17/2003. Report is also available in paper and microfiche from NTIS.

Made available in DSpace on 2014-10-09T12:37:32Z (GMT). No. of bitstreams: 0 / Made available in DSpace on 2014-10-09T14:03:17Z (GMT). No. of bitstreams: 1 05174.pdf: 4868507 bytes, checksum: ef4d7e8312562d1a1e608bf1fd65e9ec (MD5) / Tese (Doutoramento) / IPEN/T / Instituto de Pesquisas Energeticas e Nucleares, Sao Paulo

Made available in DSpace on 2015-03-13T17:08:39Z (GMT). No. of bitstreams: 1 LuizGSD_ate_cap6.pdf: 3498562 bytes, checksum: 2d2d95d878c0320cd578c1fd98d02cfe (MD5) Previous issue date: 2006-08-31 / Coordena??o de Aperfei?oamento de Pessoal de N?vel Superior / The of Serrinha plutonic suite, northeastern portion of the Borborema Province (NE Brazil), is characterized by a voluminous and diversified magmatism of Neoproterozoic age, intrusive in the Archean to Paleoproterozoic gneissic-migmatitic basement of the S?o Jos? de Campestre massif. Field relations and petrographic and geochemical data allowed us to individualize different lithologic types among this plutonic suite, which is represented by intermediate to mafic enclaves, porphyritic diorites, porphyritic granitoids, porphyritic granodiorites, microporphyritic granites and dykes/sheets of microgranite. The intermediate-to-mafic enclaves occur associated with porphyritic granitoids, showing mixture textures. The porphyrytic diorites occur as isolated bodies, generally associated with intermediate-to-mafic enclaves and locally as enclaves within porphyritic granites. The granodiorites represent mixing between an intermediate to mafic magma with an acidic one. The micropophyritic granites occur as isolated small bodies, generally deformed, while the microgranite dykes/sheets crosscut all the previous granitoids. A U-Pb zircon age of 576 + 3 Ma was obtained for the Serrinha granite. This age is interpreted as age of the peak of the regional ductile deformational event (D3) and of the associated the E-W Rio Jacu shear zone, which control the emplacement of the Neoproterozoic syntectonic plutons. The porphyrytic granitoids show monzogranitic composition, transitional between peraluminous and metaluminous types, typically of the high potassium subalkaline-calc-alkaline series. The intermediate-to-mafic enclaves present vary from quartz diorite to tonalite/granodiorite, with metaluminous, shoshonitic affinity. The diorites are generally quartz-monzodiorite in composition, with metaluminous, subalkaline affinity. They display coarse-grained, inequigranular, porphyrytic texture, with predominance of plagioclase phenocrystals immersed in a matrix composed of biotite and pyroxenes. The microporphyrytic granites are essentially monzogranites of fine- to medium-grained texture, whereas microgranite dikes/sheets varying from monzogranites to syenogranites, with fine to media texture, equigranular. The diversified magmatism occurring at a relatively small surface associated with shear zones, suggests lithospheric dimensions for such structures, with magma extractions from different depths within the lower crust and upper mantle. The geological, geochemical and geochronological characteristics of the Serrinha plutonic suite suggest a pos-collisional geodynamic context for the Neoproterozoic magmatism. Thermobarometric data show emplacement conditions in the range 5-6 kbar (AlTamphibole) and 730-740?C (plagioclase-amphibole) for the porphyrytic granitoids (Serrinha body) and the intermediate-to-mafic enclaves / A su?te plut?nica da regi?o de Serrinha, localizada no extremo nordeste da Prov?ncia Borborema (NE do Brasil), caracteriza-se por um volumoso e diversificado magmatismo de idade neoproteroz?ica, intrusivo no substrato gn?issico-migmat?tico, de idade arqueana a paleoproteroz?ica, do Maci?o S?o Jos? de Campestre. Rela??es de campo, dados petrogr?ficos e geoqu?micos permitiram individualizar os diferentes tipos litol?gicos desta su?te plut?nica, que s?o representados por encraves intermedi?rios a m?ficos, rochas dior?ticas porfir?ticas, granit?ides porfir?ticos, granodioritos porfir?ticos, granitos microporfir?ticos e diques/sheets microgran?ticos. Os encraves intermedi?rios a m?ficos ocorrem, principalmente, associados aos granit?ides porfir?ticos, exibindo fei??es de mistura. Os dioritos porfir?ticos ocorrem como corpos isolados, associados com encraves intermedi?rios a m?ficos, e localmente como encraves nos granitos porfir?ticos. Os granodioritos representam um f?cies t?pico de mistura entre um magma intermedi?rio a m?fico, dior?tico, e outro ?cido, granitico. Os granitos microporfir?ticos apresentam-se como pequenos corpos isolados, geralmente deformados. Os diques e sheets microgran?ticos s?o tardios na seq??ncia magm?tica da ?rea estudada, com rela??es intrusivas nas demais unidades magm?ticas. Uma idada U-Pb em zirc?o de 576 + 3 Ma foi obtida para o Granito Serrinha, que ocorre controlado por uma zona de cisalhamento de dire??o geral E-W (Zona de Cisalhamento Rio Jacu). Tendo em vista o car?ter sintect?nico desse pl?ton, essa idade marca a sua coloca??o e o pico da deforma??o D3 associada. Este evento ? respons?vel pela atual arquitetura estrutural da ?rea mapeada, com gera??o da tect?nica ranscorrente/distensional impressa nas zonas de cisalhamento que controlam o alojamento dos pl?tons neoproteroz?icos. Os granit?ides porfir?ticos apresentam composi??o predominantemente monzogran?tica, apresentando caracter?sticas transicionais entre peraluminosos e metaluminosos, tipicamente de afinidade subalcalina - c?lcio-alcalina de alto K. Os encraves intermedi?rios a m?ficos variam de quartzo dioritos a tonalitos/granodioritos, com textura faner?tica fina a m?dia. S?o rochas metaluminosas de afinidade shoshon?tica. As rochas dior?ticas porfir?ticas s?o principalmente quartzo monzodioritos, com textura inequigranular porfir?tica, com predom?nio de fenocristais de plagiocl?sio imersos numa matriz composta por biotita e pirox?nios. S?o rochas metaluminosas, de afinidade subalcalina m?fica. Os granitos microporfir?ticos s?o essencialmente monzogranitos de textura fina a m?dia, inequigranular, e os diques e sheetsmicrogran?ticos apresentam composi??o variando de monzogranitos a sienogranitos, com textura fina, equigranular. Apesar da pouca quantidade de dados, essas rochas apresentam caracter?sticas de afinidade geoqu?mica com a s?rie c?lcio-alcalina de alto K. O diversificado magmatismo ocorrendo em uma superf?cie relativamente pequena, associado a zonas de cisalhamento, apontam dimens?es litosf?ricas para essas estruturas, com extra??o de magmas a partir de diferentes n?veis da crosta e do manto superior. As caracter?sticas geol?gicas, geoqu?micas e geocronol?gicas da su?te plut?nica Neoproteroz?ica da regi?o de Serrinha sugerem um contexto geodin?mico p?s-colisional para a coloca??o dos corpos estudados ao final da orog?nese Neoproteroz?ica. Dados termobarom?tricos apontam condi??es P-T da ordem de 5-6 kbar (AlT-anfib?lio) e 730-740?C (plagiocl?sio-anfib?lio) para a coloca??o dos granit?ides porfir?ticos e encraves intermedi?rios a m?ficos associados

Made available in DSpace on 2014-10-09T12:37:32Z (GMT). No. of bitstreams: 0 / Made available in DSpace on 2014-10-09T14:03:17Z (GMT). No. of bitstreams: 1 05174.pdf: 4868507 bytes, checksum: ef4d7e8312562d1a1e608bf1fd65e9ec (MD5) / Tese (Doutoramento) / IPEN/T / Instituto de Pesquisas Energeticas e Nucleares, Sao Paulo

Esta tese analisa a atuação da Comissão Geográfica e Geológica do Estado de São Paulo, CGGSP no período de 1905 a 1931. Conhecer o estado de São Paulo, a sua rede hidrográfica e o seu potencial energético, a qualidade das terras para a agricultura, a localização dos núcleos urbanos e a rota de escoamento dos produtos, foi o objetivo que motivou a criação em 1886, da CGGSP. Estas metas foram alcançadas sob a chefia do engenheiro João Pedro Cardoso (1905-1931). As regiões desconhecidas no extremo oeste de São Paulo foram exploradas, a definição das divisas do estado de São Paulo teve solução definitiva, através de levantamentos sistemáticos efetuados nas regiões fronteiriças e o estado foi medido pelo método da triangulação, com a produção do mapa de São Paulo, como representação, perfeitamente levantada, demarcada e documentada. As cartas topográficas, com informações precisas sobre a localização dos rios e montanhas, das cidades e vilas, das estradas de ferro e rodoviárias, trouxeram como subproduto, as cartas gerais com dados sobre agricultura, indústria, comércio e serviços. Estudar o percurso profissional do engenheiro João Pedro, foi o fio condutor que permitiu apreciar este processo e o resultado dos trabalhos desenvolvidos pela CGGSP, instituição de excelência que, sob a sua direção, alcançou os objetivos almejados. / This thesis analyses the performance of the State of São Paulo Geographic and Geologic Commission. This Commission (CGGSP) was created in 1886 in order to better study São Paulo´s river system and energy potential, the quality of its soil, the location of urban centers and the routes for the disposal of its products. These goals were reached when the commission was headed by engineer João Pedro Cardoso (1905 - 1931). The Comission explored unknown regions in the extreme west of the state of São Paulo, defined its boundaries by systematic surveys in the frontier regions, and measured the state by the method of triangulation, with production of a map of the state of São Paulo, which was perfectly surveyed, delimited, and documented. Topographic maps with precise information regarding locations of rivers and mountains, cities and towns, and railroads and roads resulted in the elaboration of additional maps on agriculture, industry, commerce, and services. Studying the career of engineer João Pedro Cardoso allowed to appreciate how this process developed; the results of CGGSP´s work, which under his leadership became an institution known for its excellence and whose characteristics allowed it to reach its proposed goals.

Maps and models of seismic and tsunami risk are constructed from a variety of measurements taken in Indonesia, which have the potential to reduce loss of life and infrastructure. The first study uses the multichannel analysis of surface waves (MASW) method to calculate the time-averaged shear wave velocity to 30 m depth (Vs30). These measurements were taken at 58 sites in the city of Pacitan, Java and on the islands of Lombok, Ambon, and the Banda Islands. Vs30 calculations are compared with local geologic maps to extrapolate site class for locations not measured directly. Site class maps are then compared with Modified Mercalli Intensity (MMI) observations for three earthquake events that impacted Lombok and Ambon to identify regions where the MMI and Vs30 do and do not corroborate one another. Consistent with other Vs30 studies, the lowest values are observed on coastal alluvial plains and the highest values on steeper hillsides underlain by volcanic deposits. The second study focuses on a potential sector collapse of the volcano Banda Api within the Banda Islands. A field survey of its summit identified a steeply dipping normal fault striking NNE-SSW. This, along with the fissure geometry of the volcano's most recent eruption, reveals a failure plane along which a future sector collapse could occur. The numerical model Tsunami Squares (TS) predicts that the tsunami produced by this landslide would inundate an estimated 63% of buildings on the Banda Islands with waves as high as 82 m. These findings highlight the importance of installing a GPS receiver array on Banda Api to monitor the motion of its slopes. The third study analyzes sediment from trenches on the Banda Islands and Ambon to test if historical tsunamis that have impacted the area are preserved in the geological record. Potential tsunami deposits were identified by the presence of marine sand and larger clasts of marine carbonate in an environment which otherwise lacks large storms to bring such material onshore. Several dating methods constrain the ages of at least seven candidate tsunami deposits found in trenches onshore. One of these historical tsunamis (the event of November 26, 1852) is described in significant detail from several locations across the Banda Sea, which enables modeling of the event using a Bayesian statistical approach. The posterior of this model predicts the most likely epicenter was SW of Seram with a mean magnitude of Mw 8.8. It also makes other predictions about fault parameters. The region exhibits a marked slip deficit based on instrumental records of earthquakes in the area.

No description available.

<p> The BAR CLAIM GROUP is located on the western margin of the Selwyn Basin geologic province in south central Yukon. The rock sequence is eugeosynclinal in nature, belonging to the Englishman's Group of the Mississippian. Chronologically, these rocks include massive limestone, white to red chert breccia, dark grey chert breccia, chert pebble conglomerate, lithic wacke, massive barite, grey green chert, and hornblende microdiorite. The elastic units in particular appear to be correlative with the units on the eastern margin of the Selwyn Basin. </p> <p> The barite is light grey, bedded, massive, and contains rare relic rosette structures. Associated minerals include pyrite, galena and minor sphalerite. Extensive recrystallisation and mobilization has occurred, probably as a result of regional compression and faulting. The barite may have had an exhalative origin along fault or extensional zones; however, sedimentogenic sources, such as the redistribution of pre-existing barite, cannot be precluded. </p> / Thesis / Bachelor of Science (BSc)

No description available.

Geologic mapping in the Phil Pico Mountain quadrangle and analysis of the Carter Oil Company Carson Peak Unit 1 well have provided additional constraints on the erosional and uplift history of this section of the north flank of the Uinta Mountains. Phil Pico Mountain is largely composed of the conglomeratic facies of the early Eocene Wasatch and middle to late Eocene Bridger Formations. These formations are separated by the Henrys Fork fault which has thrust Wasatch Formation next to Bridger Formation. The Wasatch Formation is clearly synorogenic and contains an unroofing succession from the adjacent Uinta Mountains. On Phil Pico Mountain, the Wasatch Formation contains clasts eroded sequentially from the Permian Park City Formation, Permian Pennsylvanian Weber Sandstone, Pennsylvanian Morgan Formation, and the Pennsylvanian Round Valley and Mississippian Madison Limestones. Renewed uplift in the middle and late Eocene led to the erosion of Wasatch Formation and its redeposition as Bridger Formation on the down-thrown footwall of the Henrys Fork fault. Field observations and analysis of the cuttings and lithology log from Carson Peak Unit 1 well suggest that initial uplift along the Henrys Fork Fault occurred in the late early or early middle Eocene with the most active periods of uplift in the middle and late Eocene (Figure 8, Figure 24, Appendix 1). The approximate post-Paleocene throw of the Henrys Fork fault at Phil Pico Mountain is 2070 m (6800 ft). The Carson Peak Unit 1 well also reveals that just north of the Henrys Fork fault at Phil Pico Mountain the Bridger Formation (middle to late Eocene) is 520 m (1710 ft) thick; an additional 460 m (1500 ft) of Bridger Formation lies above the well on Phil Pico Mountain. Beneath the Bridger Formation are 400 m (1180 ft) of Green River Formation (early to middle Eocene), 1520 m (5010 ft) of Wasatch Formation (early Eocene), and 850 m (2800 ft) of the Fort Union Formation (Paleocene). Stratigraphic data from three sections located east to west across the Phil Pico Mountain quadrangle show that the Protero-zoic Red Pine Shale has substantially more sandstone and less shale in the eastern section of the quadrangle. Field observations suggest that the Red Pine Shale undergoes a facies change across the quadrangle. However, due to the lack of continuous stratigraphic exposures, the cause of this change is not known.